Portland State University Portland State University PDXScholar PDXScholar Dissertations and Theses Dissertations and Theses 1986 A stratigraphic-geochemical study of the Troutdale A stratigraphic-geochemical study of the Troutdale Formation and Sandy River Mudstone in the Portland Formation and Sandy River Mudstone in the Portland basin and lower Columbia River Gorge basin and lower Columbia River Gorge Rodney Duane Swanson Portland State University Follow this and additional works at: https://pdxscholar.library.pdx.edu/open_access_etds Part of the Geochemistry Commons, Geology Commons, and the Stratigraphy Commons Let us know how access to this document benefits you. Recommended Citation Recommended Citation Swanson, Rodney Duane, "A stratigraphic-geochemical study of the Troutdale Formation and Sandy River Mudstone in the Portland basin and lower Columbia River Gorge" (1986). Dissertations and Theses. Paper 3720. https://doi.org/10.15760/etd.5604 This Thesis is brought to you for free and open access. It has been accepted for inclusion in Dissertations and Theses by an authorized administrator of PDXScholar. Please contact us if we can make this document more accessible: [email protected].
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Portland State University Portland State University
PDXScholar PDXScholar
Dissertations and Theses Dissertations and Theses
1986
A stratigraphic-geochemical study of the Troutdale A stratigraphic-geochemical study of the Troutdale
Formation and Sandy River Mudstone in the Portland Formation and Sandy River Mudstone in the Portland
basin and lower Columbia River Gorge basin and lower Columbia River Gorge
Rodney Duane Swanson Portland State University
Follow this and additional works at: https://pdxscholar.library.pdx.edu/open_access_etds
Part of the Geochemistry Commons, Geology Commons, and the Stratigraphy Commons
Let us know how access to this document benefits you.
Recommended Citation Recommended Citation Swanson, Rodney Duane, "A stratigraphic-geochemical study of the Troutdale Formation and Sandy River Mudstone in the Portland basin and lower Columbia River Gorge" (1986). Dissertations and Theses. Paper 3720. https://doi.org/10.15760/etd.5604
This Thesis is brought to you for free and open access. It has been accepted for inclusion in Dissertations and Theses by an authorized administrator of PDXScholar. Please contact us if we can make this document more accessible: [email protected].
17. Lanthanum/samarium versus lanthanum graph for Boring
Lavas of the Portland area, high-alumina basalts of
the lower Columbia River Gorge area, and vitric
separates
18. FeO*/MgO versus Si02 graph with vitric separates
compared with High Cascades lavas . . .
19. Ti02 versus P2o5 graph comparing vitric to High
Cascades basalts Simcoe volcanics basalts ...
20. Distribution of the Troutdale Formation in the lower
Columbia River Gorge .••.• . . . . . . . . . . . . . 21. The elevation of the Sandy River Mudstone-Troutdale
Formation contact as mapped by Trimble (1963) .••
22. Diagramatic cross-section west-east from the eastern
so
51
53
58
59
margin of the well area to the Sandy River. . . . . . • 61
FIGURE
23. Diagramatic cross-section S-SW to N-NE between the
well area and Lackamas Lake •
24. Location of cross-sections in Appendix C •••
ix
PAGE
63
100
CHAPTER I
INTRODUCTION
General and Purpose
Numerous geologic studies of the Portland and lower Columbia
River Gorge areas include examinations of the sediments included in the
Troutdale Formation and Sandy River Mudstone. The earliest studies
(Bretz, 1917; Williams, 1916; Hodge, 1938; Treasher, 1942) grouped the
current Troutdale Formation and Sandy River Mudstone together as post
Columbia River basalt sediment. Later workers (Trimble, 1963;
Mundorff, 1964) divided the Troutdale Formation into two separate
stratigraphic units. The more widely recognized nomenclature is
Trimble's (1963) separation of the fine-grained lower portion of the
Troutdale Formation into the Sandy River Mudstone. The Troutdale
Formation and Sandy River Mudstone were still described as
stratigraphically undifferentiable masses of sediment, deposited by
some sort of ancestral Columbia River and local streams. Tolan and
Beeson (1984) further refined the stratigraphy of the Troutdale
Formation in the lower Columbia River Gorge by defining upper and lower
members of an ancestral Columbia River facies. Their informal upper
and lower members are based on the upward transition from deposits of
non-locally-derived gravels of the Columbia River drainage to sediment
dominated by hyaloclastic debris and basalt cobbles derived from High
Cascades lavas.
This study examines the hyaloclastic sediment that is in part
2
definitive of Tolan and Beeson's (1984) upper member Troutdale
Formation. Sediment included in the lower member of the Troutdale
Formation and the Sandy River Mudstone is examined in order to further
define the statigraphic relationships within these units in the
Portland area. Fluvial hyaloclastites, also referred to as vitric
sands (Trimble, 1963), in the upper member of the Troutdale Formation
are studied as potential stratigraphic marker beds based on minor and
trace element content and lithology. Basaltic glass (sideromelane)
clasts from hyaloclastites are analyzed in an attempt to correlate them
with possible Cascadian eruptive sources.
Within the City of Portland the Troutdale Formation hyaloclastic
sediment is found in wells drilled for the Portland Water Bureau
(Willis, 1977; Hoffstetter, 1984). Well cuttings, lithologic logs, and
geophysical logs used in this study are from wells drilled by the
Portland Water Bureau Exploratory Well Project (Willis, 1977). The
deepest and most widely distributed wells were drilled for the Portland
Water Bureau as a part of the Exploratory Well Project (Figure 1).
Selected cuttings from five of these wells were sampled, examined and
analyzed. Stratigraphic sections were measured and sampled near the
type area of the Troutdale Formation and Sandy River Mudstone along
the Sandy River (Hodge, 1938, Trimble, 1963). The reference section
for the upper and lower members of the Troutdale Formation at Bridal
Veil, Oregon (Tolan and Beeson, 1984) was also measured and sampled.
Figure 2 shows locations of samples and measured sections.
Geologic Background
Sediment studied in this report is interpreted to be younger than
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the lava flows of the middle Miocene Columbia River Basalt Group in
western Oregon based on their stratigraphic position overlying the
Columbia River basalts in the lower Columbia River Gorge (Tolan and
Beeson, 1984; Hodge, 1938) and in the Portland basin (Trimble, 1963).
The Columbia River Basalt Group overlies the upper Eocene to Miocene
Skamania Volcanics and the Oligocene to lower Miocene Eagle Creek
Formation east of Portland in the lower Columbia River Gorge. West of
the Portland area, middle Miocene Scappoose Formation and older Eocene,
Oligocene and lower Miocene marine sediments of the Yamhill Formation,
Cowlitz Formation, Keasey Formation and Pittsburg Bluff Formation along
with the Eocene basalts of the Tillamook Volcanics predate the Columbia
River basalt (Newton, 1969; Hammond, 1979; Kadri, 1982; Van Atta and
Kelty, 1985). In the Cascade Range west of Mount Hood, the middle to
upper Miocene Rhododendron Formation interf ingers with and overlies
flows of the Columbia River Basalt Group (Priest and others, 1982).
The Sandy River Mudstone and Troutdale Formation overlie mudflows of
the Rhododendron Formation in the valleys of the Sandy River and
Clackamas River (Allen, 1932; Trimble, 1963; Peck and others, 1964).
Figure 3 depicts the general Cenozoic stratigraphy in the Portland area
and lower Columbia River Gorge.
The Troutdale Formation was named by Hodge (1938) for thick beds
of gravels and sands exposed as cliffs along the Sandy River near the
town of Troutdale, Oregon. Here, the Troutdale Formation is composed
of coarse, fluvially-deposited hyaloclastites, quartzite-bearing
gravels, lenses of micaceous arkose, and lithic sands (Trimble, 1963).
Trimble (1963) determined that the hyaloclastites are composed of
SYSTEM/SERIES
QUATERNARY
Ill z Ill u 0 :; ..
:: ~ ~ ~ ;:: • c ... :I • • 0 I .
UNIT
SEDIMENTARY DEl"OSITS
CASCADIAN
SEDIMINfAllY
DEl"OSITS
i iC ...
Q Ill z Q
c ~ 0 ~ z - :c • 0 0 -• :c
• • • • • ••! I ... ___ ..,. :: : SANDY RIYH
! 5 MUDSTONE
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Ill z Ill u 0 0 :; 0
2 ~ RHODODENDRON.
: ~ FORMATION ... 0 ~ .. ...
COLUMllA RIVER
BASALT GROUP
SKAMANIA
VOLCANIC SHIES
6
Figure 3. General stratigraphic column for the Portland area and lower Columbi'8°River Gorge. Modified from Tolan and Beeson (1984), Trimble (1963), and Anderson (1980).
7
sideromelane (basaltic glass) sand based on refractive index and
attributed their formation to the interaction of basalt flows and a
river flowing through the Cascades. Figure 4 is a generalized
stratigraphic section for the type locality of the Troutdale Formation
along the Sandy River taken from Trimble (1963). Trimble (1963) noted
that beneath the gravels are beds of mud and sandy mud, possibly of
lacustrine origin, and renamed this portion of Hodge's Troutdale
Formation the Sandy River Mudstone. The Sandy River Mudstone and
Troutdale Formation extend westward into the Portland Basin where they
are presumed to overlie Columbia River basalt based on a driller's log
from the Ladd well near NE 39th and Glisan (circa 1885) and other wells
drilled near the margins of the basin (Trimble, 1963).
Fossil flora found in the Sandy River Mudstone near the
transition from the Sandy River Mudstone to the Troutdale Formation in
the Sandy River area establish an age of early Pliocene (Chaney, 1944
in Trimble, 1963 p.35). In the Portland area upper Pliocene to lower
Pleistocene Boring Lavas intrude and overlie the Troutdale Formation
unconformably (Treasher, 1942; Trimble, 1963; Beeson and Nelson, 1978).
A potassium-argon age date of 1.3 m.y.b.p. has been determined for
Boring Lavas from Rocky Butte in northeast Portland (Edwin McKee and
Norman Macleod, 1985 unpublished date, written communication). A
somewhat older age of 2.6 m.y.b.p. is found for Boring Lavas of the
Oregon City plateau (Robert Duncan and Norman MacLeod, 1985 unpublished
potassium-argon age date, written communication).
Tolan and Beeson (1984), in their work with Columbia River Basalt
Group stratigraphy of the Columbia River Gorge interpreted a thick
Cobbly and bouldery vitric sandstone
Lenticular Quartzite-bearing conglomerate and micaceous Quartzose sandstone
Fine-grained sandstone, siltstone, and claystone; leaf-bearing
Lenticular vitric sandstone and Quartzite-bearing conglomerate
Figure~ Geologic, hyaloclastic and hydrogeologic units of the well area. Figure 6a, from Hoffstetter (1984), shows the hydrogeologic units of the Portland Well Field. Figure 6b is the geologic and hyaloclastic units defined and described in this study (modified from Willis, 1977). Ttl=lower member Troutdale, Ttu=upper member Troutdale, Qgs=Quaternary gravels and sands, RC=Rose City hyaloclastic unit, TSA=Troutdale sandstone hyaloclastic unit, UTSA=upper Troutdale sandstone hyaloclastic unit. Not shown, LRC lower Rose City hyaloclastic unit 250 feet below upper Troutdale base in well 1N/2E 29DA.
13
14
lower Troutdale Formation equivalent sediment and is distinct in source
from the upper Troutdale hyaloclastic beds (RC, TSA and UTSA).
Hyaloclastic debris forms as lava advances into a body of water
or is erupted beneath water. Glass is formed by rapid chilling of
lava. In cases where lava flows into standing water such as a lake,
water trapped by advancing flow lobes turns to steam causing explosive
brecciation of the glass (Fuller, 1931). Typically, this sort of
basalt-water interaction produces brecciated glass and pillows. This
glassy material and basaltic debris tends to accumulate in place and
produce a pillow-palagonite complex with hyaloclastic debris and basalt
pillows accumulating in foreset beds.
The fluvial deposition of upper Troutdale Formation
hyaloclastites in the lower Columbia River Gorge does not resemble the
debris accumulation of a pillow-palagonite complex. A more appropriate
name for the upper Troutdale basaltic glass-rich sediment is reworked
or fluvially-deposited hyaloclastite based on the nomenclature of
Silvestri (1961). A mechanism that could form the reworked
hyaloclastites of the upper Troutdale Formation requires that the
hyaloclastic debris be actively removed from the source lavas in order
to produce the near purely hyaloclastic sedimentary beds found in the
Troutdale Formation.
Lavas erupted into a major river such as the Columbia would form
hyaloclastic debris. The river, although it may be constricted by the
lava flow entering its course, would continue to flow past the lava
flow. River flow over and around the erupting lava would continuously
produce and transport hyaloclastic debris along with crystalline
15
fragments eroded from flows and pillows. Partial damming of the river
by lavas, along with the sudden addition of hyaloclastic sediment,
could lead to the deposition of a sheet or apron of sediment
downstream. After an eruptive period it is likely that the river
channel would cut into the hyaloclastic debris sheet and rework some of
it.
It is likely that the interlayering of hyaloclastic or vitric
sands with arkosic sands, gravels and muds of the Portland Well Field
is the result of intermittent periods of high-alumina basalt eruptive
activity along the course of a river draining over a flood plain in the
Portland area. During eruptive periods basaltic hyaloclastic sediment
would choke the river system and result in the deposition of
hyaloclastites. Between major eruptive events, non-locally derived,
ancestral Columbia River sediment and mixed local and non-local
sediment would be deposited.
Geochemical Analysis
Sediment, hyaloclastite and basalt samples were analysed at
Portland State University using Instrumental Neutron Activation
Analysis (INAA). Elements detected with acceptable experimental errors
are: Na, K, Sc, Cr, Fe, Co, Cs, Hf, Ta, the rare earth elements La, Ce,
Sm, Eu, Tb, Yb and Lu, and Th. Eighty-seven samples (not including
standards) were analyzed in three experiments. Appendix A gives type
of material sampled, location, formation and member, and experiment
number for samples analyzed. Appendix B gives a more detailed
description of the analytical procedure along with data tables showing
elemental concentrations determined for each sample. Three vitric
16
separate samples were sent to Dr. Peter Hooper's x-ray fluorescence lab
at Washington State University for filajor oxide analysis.
CHAPTER II
NON-HYALOCLASTIC SEDIMENTARY ROCKS OF THE SANDY RIVER MUDSTONE
Figure .2....:.. Scandium versus cobalt graph for non-hyaloclastic sediments, o; hyaloclastic sediments and vitric separates, o; for INAA experiment 7T samples from well 1N/3E 20CD2 and field samples.
Figure 10. Scandium versus cobalt graph for sediments from below the RC and TSA hyaloclastic sediment, o; and vitric separates and palagonites, o; from wells 1N/2E 29DA and 1N/2E 31CD.
26
samples from the the upper member in well 1N/3E 20CB2, 5-135 and 5-305
fall within the lower member and Sandy River Mudstone group.
Results of INAA experiment 7H, using suites of sediment from
below the base of the obvious hyalocatic beds in wells 1N/2E 29DA and
1N/3E 31CD, indicate no sediment group characterized by higher amounts
of chromium, scandium, cobalt and iron similar to the upper sediments
in 1N/3E 20CB2. Figure 10 plots Sc versus Co for INAA experiment 7H
samples indicating no significant amount of hyaloclastic material or
other high-alumina basalt derived sediment is detected based on the
criteria established for well hole 1N/3E 20CB2.
The increases in chromium, iron, scandium and cobalt found above
sample 5-535 in well hole 1N/3E 20CB2 are similar to what might be
caused by adding high-alumina basalt-derived sediment of the
composition found in the analyzed hyaloclastites. Sediment beds in the
high chromium-scandium-iron-cobalt group are intimately associated with
the TSA and RC hyaloclastite units. The sediment chemistry group
characterized by higher concentrations of Cr, Fe, Sc and Co is evident
only down to the base of the TSA and RC hyaloclastite units. Sediment
from between the stratigraphically lowest hyaloclastite-bearing unit
(LRC) at a well depth of 1125 feet (-925 feet elev.) in 1N/2E 29DA and
the base of the TSA-RC hyaloclastites shows no Cr, Fe, Sc and Co
enrichment similar to the sediment in proximity to the TSA and RC
hyaloclastite units.
Total elemental abundances can vary with sediment texture, e.g.
mudrocks tend to have higher trace element concentrations than sands
(Haskin and others, 1966), while relative concentrations are usually
27
alike for most sediments from a similar type geologic provenance
(Bhatia and Taylor, 1981). Generally, in sediment, rare earth element
abundances tend to increase with progressively more evolved source
areas. The lowest concentrations are associated with undissected
magmatic arcs. Dissected magmatic arcs and more evolved continental
areas would have increasingly higher concentrations of rare earth
elements and thorium. More evolved continental crust rocks tend to
have lower La/Th ratios (Bhatia and Taylor, 1981; Nance and Taylor,
1976).
A graph of lanthanum versus thorium (Figure 11) was drawn to help
display possible variations in geochemistry caused by sediment
contributions from differing source areas based on the relative amounts
of these elements. Most sediment samples plotted on the lanthanum to
thorium graph fell on or near a line with a slope of 4, indicating a
relatively constant lanthanum to thorium ratio. This is near the
maximum lanthanum to thorium ratio found in fine grained sediments
(McLennan and others, 1980). Sediments from the Troutdale Formation
with the lowest total amount of lanthanum and thorium are associated
with vitric-bearing gravels and sands.
When the distribution of the Troutdale Formation and Sandy River
Mudstone samples in Figure 11 is compared to the provenance type areas
of Bhatia and Taylor (1981), the Troutdale Formation-Sandy River
Mudstone sediment appears to be most similar to the field of sediment
derived from a dissected magmatic arc.
Examination of the sediment geochemical data suggests that the
fine sediment fraction sampled (-200 mesh) is biased toward sediment
a ...
10----------------------------. 60
501 . •
•
40 • • •
··'"' ·:-·.· - ~
30 /:.~·· ""
/ ""'. I .·. \ ••
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.._ / --. --10 II '\
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..,,,. .,,,,..
/
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20 25 30
28
Figure 11. Lanthanum versus thorium for sediments from the upper and lower Troutdale Formation and Sandy River Mudstone. Stippled area represents vitric material. Tectonic classification from Bhatia and Taylor (1981); UA=undissected magmatic arc, DA=dissected magmatic arc, and DH=dissected highland.
29
derived from all portions of the drainage basin. Examination of
whole sediment samples with a binocular microscope showed that the
locally-derived volcanic sediment in the Troutdale Formation tends to
be coarser and therefore not as well represented in the finer fraction.
In extreme cases when predominately volcanic detritus is deposited,
there would a higher likelihood of detecting its presence
geochemically. This is the case with the several samples taken from
the upper portion of well 1N/3E 20CB2.
CHAPTER III
VITRIC BEDS AND THEIR USE AS STRATIGRAPHIC MARKERS
General
No single criterion served to identify specific hyaloclastite
beds. Vitric units within the well area are divided into four groups
based on statigraphic position, lithology and geochemical
characteristics, as determined by INAA. The four well area groups of
hyaloclastite and vitric material-bearing sand were assigned
abbreviated names (Figure 6) based on informal hydrogeologic unit names
of Hoffstetter (1984). The four hyaloclastic units from lower to
uppermost are the LRC, RC, TSA and UTSA. The TSA and RC hyaloclastic
units contain the bulk of the vitric material deposited in the well
area. Along with the UTSA hyaloclastic beds the TSA and RC units are
equivalent to the type Troutdale section of Trimble (1963) and the
informal upper member Troutdale Formation of Tolan and Beeson (1984).
The lower Rose City (LRC) hyaloclastite unit is not a hyaloclastite but
a sideromelane-bearing sandy gravel. The LRC is included in the lower
Troutdale Formation of the well area. Cross-sections showing
correlation of hyaloclastic units in the well area based on natural
gamma logs, trace element geochemistry and lithology are compiled in
Appendix C.
The TSA unit can be found in all wells sampled in this study.
Other vitric beds are missing in at least one hole. Material of the
upper Troutdale sandstone aquifer (UTSA) unit is not found in holes
31
1N/3E 33AD or 1N/3E 20CB2 in the eastern portion of the well area.
Here it appears to have been either removed or not deposited prior to
deposition of the Parkrose gravel aquifer. Well 1N/2E 29DA, which has
the thickest section of vitric-bearing sediments, does not appear to
have a Rose City (RC) hyaloclastite unit. However, some sediment in
well 1N/2E 29DA below sample 1-715, which may be correlative with the
Rose City (RC) hyaloclastite, was not available for analysis due to
circulation loss during drilling. The LRC is a geochemically unique
hyaloclastic debris-bearing sandy gravel in well 1N/2E 29DA at the
1150-foot to 1120-foot well depth and possibly in trace amounts in a
gravel at 945 foot level in well 1N/3E 31CD.
Hyaloclastite Lithology
Unpalagonitized well area beds consist of medium to coarse
grained subangular to subrounded, very dark brown vitric sand or in
many cases vitric sand mixed with arkosic sand, mud and gravel. The
only macroscopic lithologic difference between the well area
hyaloclastite units is finer grain size and the presence of
palagonitization in some of the beds. Most vitric grains have a very
thin bluish-gray to light brown rind or veneer. Tiny clear to light
yellow clusters of plagioclase and olivine crystals can be seen with
the unaided eye or a 10-power hand lense.
In outcrop, vitric sands or hyaloclastites appear much more
weathered and palagonitized than those encountered by well drilling in
the Portland basin. Outcrop hyaloclastites are usually deep rusty
brown or red to orange and sometimes yellow and pink in color. In many
outcrops only small cores of sideromelane glass remain unpalagonitized.
In some beds orange-yellow pumice clasts are mixed with vitric and
crystalline grains.
32
Palagonite is a term coined to describe a yellow to brown waxy
substance found in basaltic tuffs near Palagonia, Sicily (von
Waltershausen, 1845, in Fisher and Schmincke, 1984, p.314) that is
commonly applied to altered elastic or fragmental basaltic glass
deposits. Palagonitization takes place under various temperature and
chemical conditions ranging from hydrothermal alteration to surficial
weathering processes (Fisher and Schminke, 1984). Non-marine, low
temperature palagonitization takes place rapidly above the water table
in percolating groundwater, and produces clays, zeolites, calcite and
opal (Hay and Iijima, 1968). Below the water table, palagonitization
takes place much more slowly (Christensen and Gilbert, 1964 in Hay and
Iijima, 1968). The clear, glassy unpalagonitized character of most
buried well area hyaloclastites suggests that they were buried before
they were affected by appreciable weathering and palagonitization.
Hyaloclastite Petrography
Several grain mount slides and thin sections, made from
geochemically analyzed vitric separate samples, were examined using a
petrographic microscope. Sideromelane grains in thin sections made
from well area TSA and RC bed sediment cuttings are indistinguishable
based on estimated percentages of crystals present and textural
characteristics. Outcrop samples from the Sandy River area and the
Bridal Veil Channel were nearly identical to the TSA and RC well
samples. All are dark brown glass with tiny tabular and lath shaped
plagioclase crystals, clusters of olivine grains and very small, well-
33
formed olivine crystals in the glass groundmass. The geochemically
unique sample from the LRC, sample l-1125G, is petrographically similar
to the other hyaloclastites examined.
Sample BV-9, the uppermost sample that was geochemically analyzed
from the Bridal Veil section, is composed predominantly of clasts of
subophitic olivine basalt. Red iddingsite occurs as rinds on the
olivine and as smaller grains in the matrix. Iddingsite is an
alteration following olivine (Deer and others, 1966). Red iddingsite
occurs commonly in high-alumina basalts of the High Cascades and the
Boring Lavas (Peck and others, 1964; Trimble, 1963; Wise, 1969).
However, iddingsite has not been found to be abundant in the
hyaloclastic clasts petrographically examined.
Hyaloclastite Geochemistry
Thirty-four well area and outcrop samples of hyaloclastic and
lithic sand were analyzed using INAA. In most samples, weathered
hyaloclastites and vitric-bearing sediment were manually picked for
clean unweathered glass clasts. Unweathered glass was separated to
provide a sample composed exclusively of fresh basaltic glass to avoid
possible weathering and alteration effects on trace element
concentrations. Several well cutting samples and outcrop samples in
INAA experiments 7T and 7K are cemented, palagonitic hyaloclastites or
lithic sands for which it was impractical or impossible to separate the
glass from the rest of the sample. In these cases the entire rock
sample was analyzed.
A more complete description of the analytical procedure and a
complete table of results is in appendix B. Results of geochemical
34
analyses are given in Table II. Appendix A lists sediment type,
location, and stratigraphic unit for all the analyzed vitric samples
and Plate I shows the stratigraphic position of the samples. Major
oxide contents for representative vitric separates from the TSA, RC and
LRC vitric units are in (Table III).
Geochemically, as well as lithologically, the hyaloclastite units
appear to come from very similar source material. Major oxide
geochemical data indicate that the TSA and RC vitric separates are
derived from high-alumina basalts. The RC and TSA units are,
essentially, geochemically indistinguishable from each other except for
a tendency toward slightly higher chromium concentration (about 10%
higher) in the TSA hyaloclastite. The UTSA unit is unique in its lower
Cr, Na and K content and higher amounts of light rare earth elements.
Figure 12, a graph of chromium versus lanthanum/samarium shows
variation within the group.
Due to its uniquely deep stratigraphic position a vitric separate
from l-1125G was sent for major oxide analysis to determine if it was
derived from a Columbia River Basalt Group flow postdating those found
in western Oregon. Major oxide chemistry shows the sample l-1125G
vitric material to be a high-alumina basalt dissimilar to the TSA-RC
material. Higher concentrations of titania (TiOz) and P2 05 set the LRC
apart from the TSA-RC vitric material (Figure 19).
Vitric sand from stratigraphic sections along the Sandy River and
Bridal Veil channel appear to be geochemically and lithologically
indistinguishable from the TSA and probably the RC vitric units of the
well area. The higher chromium concentration in the outcrop samples is
Figure 15. Lanthanum/samarium versus cobalt for Troutdale Formation vitric separates and Boring Lavas of the Portland area. Boring Lava data from (Darolyn Burch, 1980 unpublished manuscript).
6·
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..... ~.
40 50 60
Figure 16. Lanthanum/samarium versus cobalt for Troutdale Formation vitric separates, Columbia River Gorge area high-alumina lavas, and lower Columbia River Gorge area high-alumina basalts. Gorge basalt data from Hammond and Korosec (1983).
Figure 18. FeO*/MgO versus Si02 for vitric separates and Hood River palagonite complex basalt. Fields of upper and lower Pliocene lavas from Priest and others (1982) using data from Wise (1969).
52
The LRC vitric separate sample is unique from all analyzed High
Cascades Group lavas in Northern Oregon (Wise, 1969; Tolan and Beeson,
1984; Gannett, 1982; Priest, 1982). It is set apart by much higher
titania (Ti02 ) content (2.42%) and relatively high P205 content (.42%).
The LRC sample is, with 53.9% Si02, on the border between basaltic and
basaltic andesite. In appearence the LRC sample is no different than
the other unweathered hyaloclastic material.
The LRC's stratigraphic position 300 feet below the TSA-RC beds
in the well area and its unique geochemistry indicate that it is
probably from an eruptive source distinct in origin and time from those
of the TSA-RC hyaloclastites. Comparison of the one major oxide
analysis of the LRC glass sample to available data from the Columbia
River Gorge and the northern Oregon and southern Washington Cascade
Range leads to a tentative correlation with two flows (4.5 and 7.5
m.y.b.p.) in the Simcoe Volcanics (James Anderson, 1985 written
coITLmunication). Figure 19, Ti02 versus P205 shows a separation of the
LRC, and Simcoe Volcanics basalts similar to the LRC, from the TSA, RC,
Columbia River Gorge and Mount Hood area basalts. It is possible that
LRC glass is from a source outside the immediate area of the ancestral
Columbia River. McBirney and White (1982) described Pliocene volcanism
in central and eastern Oregon and southwestern Idaho that could produce
basalts similar to the LRC glass.
The basaltic composition of the TSA-RC hyaloclastite units argues
that a source area should contain primarily basaltic rocks. Other
limiting geochemical criteria are the very low potassium (.02% to .20%
K20), low FeO*/MgO ratios, and rare earth element concentrations (5 ppm
• • <;) • • MT HOOD(•) and \ • 0 :• / LOWER COLUMBIA RIVER
• • • / GORGE«:)) ' . / ' _../ -:.. -
--. .2 .3
P20s
--..
.4 . .5 .6
Figure 19. TiOz versus P205 comparing vitric separates to fields of Wise's (1969) Pliocene basalts; and lower Columbia River Gorge highalumina basalts of Tolan and Beeson (1984) and Goff (1977), 0; and Simcoe volcanics basalts (Anderson, 1985 written communication). Vitric separate symbols as in Figure 18.
54
La, <.05 ppm Th) of the TSA-RC units. Very few available analyses show
rocks with such low concentrations of these incompatible elements.
Examination of the most thorough study of the northern High
Cascades lavas in the Mount Hood area (Wise, 1969), indicates that few
of the eruptive centers examined by Wise (1969) are dominated by
basaltic rocks. Those eruptive centers that are primarily basaltic are
grouped stratigraphically within the ''upper Pliocene" rocks with K-Ar
ages between 4 and 2 m.y.b.p. (Figure 13, 5-2 m.y.b.p. Priest, 1982).
Two areas in which predominantly basaltic rocks were found are Lookout
Mountain on the east side of the Hood River fault, east of the Hood
River Valley and in the Bull Run area (Wise, 1969). These lavas are
not as characteristically low in K20 as the TSA-RC appear to be. They
may represent similar or contemporaneous lavas to those that are the
source of the TSA-RC hyaloclastites.
Basalts along the Columbia River Gorge near the city of Hood
River, Oregon are most similar to the TSA-RC hyaloclastites. These
include basalt and glass taken from the pillow-palagonite complex near
the base of Mount Defiance and lava from near the base of Underwood
Mountain and Beacon Rock. Basalts east of the palagonite complex
(Goff, 1977) at the West Hood River exit and Panorama Point, southeast
of Hood River are similar to, if not exactly the same as the vitric
units. Also, several very low K20 basalts were found among high
alumina basalts sampled in the Columbia River Gorge by Tolan and Beeson
(1984). These were flows overlying or interbedded with upper member
Troutdale Formation.
Beeson and Moran (1979) stated that the Hood River Mount Defiance
SS
basalts dip 10 degrees eastward toward the Hood River Fault. The Hood
River Fault has been dated as post 3 m.y.b.p. (Beeson and Moran, 1979)
because it off sets and displaces upper Pliocene basalts that were
potassium-argon age dated at 3 m.y.b.p. by Wise (1969) on Lookout
Mountain. Beeson and Moran estimated the age of these eruptions to be
near to 3 m.y.b.p., however, they could be older. Hammond and Korosec
(1983) list chemical data and potassium-argon age dates for high
alumina basalts similar to the TSA-RC in the Indian Heaven area of the
southern Washington Cascade Range. An age of 3.7 m.y.b.p. is assigned
to the basalt of Thomas Lake. While these basalts may not be suggested
as sources for the TSA-RC hyaloclastic debris, the Indian Heaven
basalts illustrate the geographic extent of volcanism similar to that
which produced the TSA and RC units.
To summarize, the basaltic glass clasts that compose the
hyaloclastite beds of the TSA and RC found in the well area and the
upper member Troutdale Formation found along the Sandy River and the in
the Bridal Veil Channel are derived from "upper Pliocene" High Cascade
Group basalts that were erupted between the Hood River Valley and the
lower Columbia River Gorge. The age of these basalts based on the
nomenclature of Wise (1969) modified by Priest (1982) is between S
m.y.b.p. and 2 m.y.b.p. The age of Hood River area basalts that are
correlable with the TSA-RC is estimated to be between S and 3 m.y.b.p.
(Beeson and Moran, 1979; Marvin Beeson, 1986 personal communication).
The LRC vitric material is similar to basalts in the Simcoe Volcanics
with ages ranging from 7.S m.y.b.p. to 2(?) m.y.b.p. The LRC is
separated from the base of the TSA-RC beds in the well area by
··--.
approximately 300 feet suggesting that timing of 7 to 3 m.y.b.p. for
deposition of the LRC unit and 5 to 3 m.y.b.p. for deposition of the
TSA-RC unit are not unreasonable.
56
CHAPTER V
STRUCTURAL DEFORMATION OF THE TROUTDALE FORMATION
Lack of recognizable stratigraphic horizons and limited areas of
exposure have hindered perception of structural deformation within the
Troutdale Formation and the Sandy River Mudstone. The Sandy River
Mudstone, and lower and upper members of the Troutdale Formation have
been described by most workers as relatively undisturbed sediment
filling a westward deepening basin in the Portland area. General
eastward thinning of the Troutdale Formation and eventual disappearence
of Troutdale Formation sediment toward the crest of the Cascade Range
is noted by several authors (Barnes and Butler, 1930; Allen, 1932;
Lowrey and Baldwin, 1952; Hodge, 1938; Trimble, 1963) (Figure 20).
Trimble (1963) used the transition of Sandy River Mudstone to Troutdale
Formation as a stratigraphic and structural marker. Using this marker,
he found regional dips of about two degrees westward into the Portland
Basin (Figure 21).
A more detailed stratigraphic interpretation of the Troutdale
Formation in the lower Columbia River Gorge and Portland area is
allowed by the recognition of stratigraphic upper and lower members
(Tolan and Beeson, 1984) within the ancestral Columbia River facies.
Delineation of the TSA, UTSA and RC hyaloclastite units as a marker
horizon within the Portland basin further refines the stratigraphy of
the Troutdale Formation for use in structural interpretation. Along
the Sandy River, Trimble's (1963) Sandy River Mudstone-Troutdale
CA
LE
""' -~
BO
Rt
.. ~
a: •.
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G
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EA
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Fig
ure
20.
D
istr
ibu
tio
n o
f th
e T
rou
tdal
e F
orm
atio
n i
n t
he
low
er
Col
umbi
a R
iver
Gor
ge.
From
A
llen
(1
93
2).
Vl
00
45· 30· l?'{{f{m'~ I -· w .. - .. ~··~.S
I
l'lea& ......
r ~··-----···-.
·...r t
45°15' _, '
5 0
CONTOUR INTERVAL 100 FEET
59
122°15'
5 MILES
Figure 21. The elevation of the Sandy River Mudstone-Troutdale Formati~contact as mapped by Trimble (1963). Modified from Trimble (1963).
60
Formation contact appears to be equivalent to Tolan and Beeson's (1984)
lower to upper Troutdale Formation transition in the Bridal Veil
channel. Within the well area the upper member Troutdale Formation
hyaloclastic beds define an interval within the muds, sands and gravels
of the Troutdale Formation and Sandy River Mudstone equivalent
sediments.
Based on the distribution of the upper Troutdale Formation
hyaloclastite beds in the lower Columbia River Gorge the relative
uplift between the Portland basin and Cascade Range along the Columbia
River Gorge can be determined. About 800 feet of uplift is found
between the the mouth of the Sandy River area and the Bridal Veil
channel 10 miles to the east. Wells in the easternmost portion of the
well area show the base of the RC to be at about -500 feet (wells:
equivalents near the mouth of the Sandy River 4 miles to the east.
The Troudale Formation and Sandy River Mudstone appear to dip
shallowly westward from the Sandy River area to the eastern margin of
the well area (Figure 22). The cross-section in Figure 22 is based
upon exposures along the Sandy River and the stratigraphy within the
well area. The uppermost hyaloclastite units are truncated by the
overlying Troutdale Formation gravels in the eastern part of the the
well area. This may indicate that the western portion of the well area
was moving downward relative to the eastern portion at the time the
latest Troutdale Formation sediments were being deposited (Figure 22).
Deformation of the sediments is inferred (Trimble, 1963) to be
the result of post-depositional uplift in the Cascades and possibly
Wes
t
Wel
l
1N
/3E
31
CD
Wel
l
1N
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33
AD
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t'
A
East
~
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50
0
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----
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---
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--
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.--
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Ttl
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Vert
ical
ex
ag
gera
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5X
Ele
vati
on
in
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et
---
---
0 1
2 3m
lle1
Fig
ure
2
2.
Dia
gra
mat
ic c
ross
-secti
on
west
-east
fr
om
the
east
ern
m
arg
in o
f th
e w
ell
are
a
to
the
San
dy
Riv
er.
Wel
l lo
gs
from
Wil
lis
(19
77
),
geo
log
y m
od
ifie
d aft
er
Tri
mb
le
(19
63
).
--
--5
00
-10
00
Qsg
Q
uat
ern
ary
gra
vel
and
sand
Ttu
u
pp
er m
embe
r T
rou
tdal
e F
orm
atio
n
UTS
A
TSA
H
yalo
cla
ati
c
sed
imen
t b
eds
RC
Ttl
lo
wer
mem
ber
Tro
utd
ale
Fo
rmat
ion
Tsr
S
andy
Riv
er M
udat
one
°' 1--'
62
some downwarping of the synf ormal structure of the Portland basin
during deposion of the sediments. Beeson and others (1985), working
with Columbia River Basalt Group stratigraphy, interpret the Portland
Basin to be a pull-apart basin caused by right-lateral wrench faulting
related to the Portland Hills-Clackamas River Fault Zone, active since
at least middle Miocene time. The shallow basin that collected the
Troutdale Formation and Sandy River Mudstone extends east of the Sandy
River into what is now the western foothills of the Cascade Range.
While the current rhomoidal Portland basin appears to be a more recent
occurrence.
A monoclinal fold with a northwesterly axis is located between
the well area near Blue Lake and Prune Hill, northwest of Camas,
Washington. This structure postdates the upper Troutdale Formation
hyaloclastic beds and may be associated with the formation of the
currently existing Portland basin. Beds of TSA equivalent
hyaloclastite, dipping 10 to 15 degrees to the southwest, form cuesta
like ridges at Taggart Bluff on the south shore of the Columbia River
and along the south shore of Blue Lake. Reconnaissance mapping in the
Prune Hill area identified an approximately 200-foot section of nearly
flat-lying fluvial hyaloclastic sediCTent and gravelly vitric sand,
exposed between elevations of 450 feet to 650 feet on the south side of
Prune Hill that are lithologically similar to the TSA sediment of the
well area.
A cross-section through this area shows a monclinal fold with
beds truncated by the Columbia River (Figure 23). Davis (1986
unpublished Portland State University masters thesis manuscript)
s-sw
fb.
y . ..
\ .q,
'Y
ci
N-N
E
J
0
-soo
-10
00
Ttu
, Q
sg
Well
1N
/3E
20
CB
2
• '&
jl
O'
v T
SA
--
.,
. /
-:;--
Qsg
/
TSA
--
RC
Ttl
-Tsr
Tcr?
T
sv?
,,
--
,,
"""-
/ /
- -.,._,,
/ /
/
"" -
Vert
ical
ex
ag
gera
tio
n
SX
Ele
vati
on
in
fe
et
Tsv
0 1
2 3m
lle1
Pru
ne H
ill
--
RC
--
--Jn
Qsq
Q
uat
ern
ary
gra
vel
and
sa
nd
Ttu
u
pp
er m
embe
r T
rou
tdale
Fo
rmat
ion
U
TSA
Tt;
l
Tsr
Tcr
Tsv
TSA
H
yalo
cla
stic
se
dim
ent
bed
s RC
low
er m
embe
r T
rou
tdale
Fo
rmat
ion
San
dy R
iver
Mud
ston
e
Col
umbi
a R
iver
B
asa
lt G
roup
Ska
man
ia V
olc
anic
Seri
es
Fig
ure
23.
D
iag
ram
atic
cro
ss-s
ecti
on
S-S
W
to N
-NE
betw
een
the
wel
l ar
ea a
nd
Lac
kam
as
Lak
e.
Wel
l lo
gs
from
Wil
lis
(19
77
),
geol
ogy
mod
ifie
d fr
om T
rim
ble
(196
3)
and
Mun
dorf
f (1
96
4).
0 -soo
-10
00
0\ w
64
performed a gravity survey across the northwest-southeast-trending
Lackamas Lake lineament. Using the large density difference between
the Troutdale Formation and the underlying Columbia River basalts and
Skamania Volcanics Davis modeled several northwest-trending block
faults which cut the Columbia River basalts and presumably overlying
Troutdale Formation and Sandy River Mudstone near the eastern border of
the Portland basin and along the Lackamas Lake lineament.
Displacements are estimated to be up to 400 feet (Davis, 1986). The
400 to 500 foot displacement of the upper Troutdale Formation between
the well area and Prune Hill agrees with the magnitude of this probable
fault displacement.
The Blue Lake-Prune Hill deformation near the northeast margin of
the Portland Basin may be associated with the eruption of the Boring
Lavas in the Portland area. Beeson and others (1975) suggest that
Boring Lava volcanism in the Portland area is related to deformation
along the Portland Hills fault. Available potassium-argon age dates
for Boring Lavas of 2.6 m.y.b.p. for the Oregon City plateau and 1.3
m.y.b.p. at Rocky Butte (Norman MacLeod, Robert Duncan, and Edwin
McKee, 1985 written communication,) suggest that these rocks were
erupted in the very latest Pliocene to early Pleistocene.
This study finds that the Portland basin has been tectonically
active during and after the deposition of the Sandy River Mudstone and
Troutdale Formation. The basin appears to have thickened to the west
as upper Troutdale Formation sediment accumulated in the late
Pliocene(?). Post TSA-RC displacement defines the northeastern margin
65
of the Portland basin in its current form. Several hundred feet of
deformation is seen in the hyaloclastic beds of the upper member
Troutdale Formation between the well area south of Blue Lake and
exposures of equivalent strata across the Columbia River at Prune Hill.
More gradual deformation is seen between the well area and the
Troutdale Formation along the lower Sandy River area.
CHAPTER VI
LATE CENOZOIC GEOLOGIC HISTORY OF THE PORTLAND BASIN
Outcrop patterns mapped by Trimble (1963) and Tolan (1982)
suggest that the Columbia River Basalt Group lava flows were deposited
around hills of the older Eocene to Miocene Skamania Volcanics.
Columbia River basalt flows apparently entered the Portland area via a
trough in the northern Oregon Cascades (Beeson and Moran, 1979). Flows
passed through western Oregon and into the shallow marine sediments of
the Miocene northern Oregon coast (Beeson, Perttu and Perttu, 1979).
Trimble (1963) interpreted 400 feet of rock, logged at the bottom
of the Ladd Well in southeast Portland, to be Columbia River basalt. A
well drilled for the City of Fairview encountered basalt interpreted to
be Columbia River basalt at -670 feet elevation and other rocks
interpreted to be pre-Columbia River basalt rocks (Foxworthy and
others, 1964). The youngest Columbia River Basalt Group flow mapped
in western Oregon is the Pomona flow which occurs as an intracanyon
flow patially filling the Bridal Veil channel of Tolan and Beeson
(1984). This channel, was cut into older Columbia River Basalt Group
flows (Tolan and Beeson, 1984). Deformation of the Columbia River
basalts was occurring in the Portland area at the time of basalt
deposition, but little sediment accumulation occurred (Beeson and
others 1975; Beeson and others, 1985).
As Columbia River basalt volcanism ended in late Miocene time,
deformation continued. Muds and sandy muds equivalent to the lower
67
member of the Troutdale Formation and the Sandy River Mudstone
accumulated in a basin which apparently extended from the eastern base
of the Tualatin Mountains to east of the present-day Sandy River. At
the same time in the Cascade Range, an ancestral Columbia River
deposited sandy gravels in the confined canyon of the Bridal Veil
channel. Also, at this time, volcaniclastics equivalent to the upper
Rhododendron Formation were deposited within the lower member Troutdale
Formation in the Bridal Veil Channel. No Rhododendron Formation
volcanic units are found in the well area sediments.
The hyaloclastic debris-bearing gravel LRC bed is the first
evidence of Pliocene high-alumina-volcanism-derived sediraent deposited
in the Portland basin. Vitric material from the LRC bed (sample l-
1125G) is derived from lavas of the Simcoe Volcanics, 7 to 2 m.y.b.p.,
in the Goldendale, Washington area.
Cascadian high-alumina basalts erupted during the early Pliocene
(5 to 2 m.y.b.p.) interacted with the ancestral Columbia River to form
the fluvially deposited hyaloclastites of the RC, TSA and upper TSA
units. Basalts similar to the TSA-RC hyaloclastites are found in an
area from the Hood River Valley to the Bull Run area. A high-alumina
basalt flow with chemistry similar to the TSA-RC is found within the
upper member Troutdale Formation at Bridal Veil. An exposed pillow
palagonite complex along Interstate Highway 84 just west of the city of
Hood River, Oregon suggests interaction of lava with a lake (Waters,
1973).
After the uppermost hyaloclastite beds were deposited, another
episode of deformation took place. Upper Troutdale Formation sediment
68
consisting chiefly of gravels that are mixed Columbia River sediment
and volcanic lithic clasts apparently derived from the Cascade Range
accumulated to at least what is now about 600 to 700 feet elevation in
the Portland area. Rocky Butte, Mount Tabor, Kelly Butte and Powell
Butte all are partially composed of post hyaloclastite gravels
recognized to be Troutdale Formation (Trimble, 1963; Treasher, 1942).
Reconnaissance mapping of Troutdale Formation outcrops in the
Lackamas Lake-Prune Hill area, Washington indicates that 400 to 500
feet of downward displacement has occurred within the upper Troutdale
Formation between Prune Hill and the Blue Lake area. The rectangular
shape of the Portland Basin as it exists today appears to be the result
of this period of tectonic activity.
A period of erosion appears to have followed deposition of the
Troutdale Formation sediments and preceded eruption of the Portland
area high-alumina basalts (Boring Lavas). Lavas near Prune Hill,
Washington are at lower elevations than near-by upper member Troutdale
Formation hyaloclastites. A similar exa~ple is found on the west of
Rocky Butte.
An approximate upper age of under 2 m.y.b.p. is placed on the
Troutdale Formation based on the stratigraphic relationship between the
Troutdale Formation and Boring Lava vents in the Portland area. Boring
Lavas intrude and apparently have deposited scoria and ash within or on
the Troutdale Formation at Rocky Butte, Mount Tabor, Kelly Butte and
Powell Butte. The Boring Lava at Rocky Butte has been radiometrically
dated at 1.3 m.y.b.p. (Edwin McKee and Norman MacLeod, 1985 written
communication).
Pleistocene sediments were deposited onto an uneven, eroded
Troutdale Formation surface. The oldest Pleistocene sediment is the
apron-like deposit of Cascadian gravels and mudflows of the
69
Springwater Formation and Walters Hill Formations (Trimble, 1963).
These rocks were previously included in the Troutdale Formation
(Treasher, 1942) because of their similarity to the uppermost Troutdale
Formation and deep weathered horizon.
During the remainder of the Pleistocene, the Troutdale Formation
and Sandy River Mudstone continued to be eroded in the Portland area
and several episodes of sediment deposition and removal took place
(Trimble, 1963).
CHAPTER VII
SUMMARY AND CONCLUSIONS
Hyaloclastic sediments that characterize the Troutdale Formation
are present in wells drilled for the Portland Water Bureau in the
Portland basin. Four separate hyaloclastic units were identified in
the well area based primarily on stratigraphic position, along with
geochemical composition and lithology. The bulk of the hyaloclastic
material is contained in the three upper hyaloclastic units (the RC,
TSA and UTSA). These three hyaloclastic units form a geochemical and
lithologic group that is correlative with both the informal upper
member Troutdale Formation of Tolan and Beeson (1984) in the Bridal
Veil channel and the type area of the Troutdale Formation along the
Sandy River. The well area RC and TSA are distingiushed by beds rich
in unweathered plagioclase and olivine-bearing sideromelane grains.
The TSA and RC units contain most of the hyaloclastic debris deposited
in the well area. The UTSA is the uppermost hyaloclastic debris
bearing unit. It is found in the western and southernmost portion of
the well area. The UTSA is generally beds of orange-brown to grayish
cemented palagonite. The fourth hyaloclastic unit (LRC) is a
hyaloclsatic debris-bearing sandy gravel within well area sediment
equivalent to the Sandy River Mudstone and lower Troutdale Formation.
The LRC is geochemically as well as stratigraphically distinct from the
upper Troutdale Formation hyaloclastic beds.
Hyaloclastic units, defined as a diagnostic component of Tolan
71
and Beeson's (1984) upper member of the Troutdale Formation can be used
as a stratigraphic marker within the Troutdale Formation of the lower
Columbia River Gorge and the up to 1700 feet of upper Miocene and
Pliocene sediments in the Portland basin. This interval is 300 to 400
feet thick in the well area and up to 500 feet thick in the Bridal Veil
channel. The lower Troutdale Formation to upper Troutdale Formation
transition within the well area is the base of the RC-TSA-UTSA
hyaloclastic debris-bearing sediment.
The hyaloclastic beds probably formed susequent to the confluence
of high-alumina basalt lavas with an ancestral Columbia River.
Hyaloclastic debris formed during the interaction of lava flows and
river water. This elastic debris and fragments of lava were washed
downstream and deposited in the Bridal Veil canyon and the Portland
basin. The upper Troutdale Formation hyaloclastite units (the UTSA,
TSA and RC) are derived from Pliocene high-alumina basalt lavas erupted
in the Cascade Range of northern Oregon and/or southern Washington.
The LRC glass clasts from the lower member are similar geochemically to
the Simcoe Volcanics in southcentral Washington.
According to Trimble (1963) and Tolan and Beeson (1984), much of
the non-hyaloclastic sediment of the Troutdale Formation was deposited
by an ancestral Columbia River. Modern Columbia River sediments from
The Dalles to the Sandy River over-lap sediment samples from the
Troutdale Formation and Sandy River Mudstone on a Q-F-L diagram. Trace
element geochemistry and petrography show the Troutdale Formation and
Sandy River Mudstone sediment to be similar to sediments derived from
dissected magmatic arc and continental rocks. Well area sediments
72
below the TSA and RC are similar geochemically and petrographically to
Sandy River Mudstone and lower member Troutdale Formation. Sediment
from within the interval bearing TSA and RC hyaloclastic beds appears
to be more lithic-rich than the sediment cuttings below this interval
and outcrop samples of Sandy River Mudstone and lower member Troutdale
Formation. However, there may be some beds of less lithic Columbia
River sediment within the interval that contains the RC, TSA and UTSA.
Upper Troutdale Formation hyaloclastites were deposited in a
shallow basin, west of the Cascade Range, extending from the Portland
area to east of the present-day Sandy River. Hyaloclastic debris was
apparently deposited in broad fans or sheets dowstream from the
confluence of lava flows by an ancestral Columbia River. The areal
extent of this basin is probably similar to the area mapped by Trimble
(1963) as Sandy River Mudstone and Troutdale Formation.
The age of formation of the Portland basin is uncertain. Beeson
and others (1985) suggested that wrench faulting related to the
Portland Hills-Clackamas River Fault Zone, active since mid-Miocene,
formed the Portland Basin. The absence of Rhododenron Formation rocks
within the well area sediments suggests that they were deposited after
Rhododendron Formation volcanism ceased at approximately 10(?) m.y.b.p.
The LRC bed, possibly within 200 feet of the base of the post-Columbia
River basalt sediment is derived from volcanism which is uppermost
Miocene and Pliocene, suggesting that most of the Portland basin
sediment is Pliocene in age.
The rhomboidally-shaped Portland Basin, extending eastward from
the eastern base of the Tualatin Mountains and encompassing the
73
Portland and Vancouver area, was still forming after the deposition of
the upper member of the Troutdale Formation. The deformation that
resulted in approximately 400 feet of downward displacement between
sediments at Prune Hill, Washington and Blue Lake directly across the
Columbia River may be tied to Boring Lava volcanism in the Portland
area. An age range of 2.6 m.y.b.p. to 1.3 m.y.b.p. has been
established from two K-Ar age dates for this period of volcansim.
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, 1980, Pomona Member of the Columbia River Basalt ~~~........-~~~-=
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75
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Furnes, H., 1978, Elemental mobility during palagonitization of a surficial hyaloclasite in Iceland: Chemical Geology, vol. 22, pp. 249-264.
76
Gannett, M., 1982, A geochemical study of the Rhododendron and The Dalles Formations in the area of Mount Hood, Oregon: M. S. thesis (unpulished), Portland State University, Portland, Oregon, 70 p.
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-~~~~~~
, 1980, Reconnaissance geologic map and cross-sections of the Southern Washington Cascade Range, latitude 45 30'-47 15' N, longitude 120 45'-122 22.5' W: Department of Geology, Portland State University, Portland, Oregon, 2 sheets, 1:125,000, 31 p.
Hammond, P. E., and Korosec, M. A., 1983, Geochemical analyses, age dates, and flow-volume estimates for Quaternary volcanic rocks, southern Cascade Mountains, Washington: Washington Division of Geology and Natural Resources Open File Report 83-13, 36 p.
Haskin, L. A., Wildeman, T. R., Frey, F. A., Collins, K. A., R., and Haskin, M. A., 1966, Rare earths in sediments: of Geophysical Research, vol. 71, pp. 6091-6105.
Keedy, C. Journal
Hay, R. L., and Iijima, A., 1968, Nature and origin of palagonite tuffs of the Honolulu Group on Oahu: Geological Society of America Memior 116, pp. 331-376.
Hodge, E.T., 1938, Geology of the lower Columbia River: Geological Society of America Bulletin, vol. 49, no. 6, pp. 831-930.
Hoffstetter, W. H., 1984, Geology of the Portland Well Field: Oregon Department of Geology and Mineral Industries, Oregon Geology, vol. 46, no. 6, pp. 63-67.
Huntting, M. T., Bennet, W. A.G., Livingston, V. E. Jr, and Moen, W. S., 1961, Geologic map of Washington: Washington Department of Natural Resources Geologic Map, 2 sheets, 1:500,000.
Kadri, M. M., 1982, Structure and influence of the Tillamook uplift on the stratigraphy of the Mist area, Oregon: M. S. thesis (unpublished), Portland State University, Portland, Oregon, 105p.
Lowry, W. D., and Baldwin, E. M., 1952, Late Cenozoic geology of the lower Columbia River Valley, Oregon: Geological Society of America Bulletin, vol. 63, no. 1, pp. 1-24.
McBirney, A. R., and White, C. M., 1982, The Cascade Province: in Thorp, R. S. ed., Orogenic Andesites and Related Rocks, John Wiley and Sons, pp. 115-135.
McBride, E. F., 1963, A classification of the common sandstones: Journal of Sedimentary Petrology, vol. 33, pp. 664-669.
77
McLennan, S. M., Nance, W. B., and Taylor, S. R., 1980, Rare earth element-thorium content in sedimentary rocks and the composition of the continental crust: Geochimica et Cosmochimica Acta, vol. 44, pp. 1833-1839.
Miyashiro, A., 1974, Volcanic rock series in island arcs and active continental margins: American Journal of Science, vol. 274, pp. 321-355.
Mundorff, M. J., 1964, Geology and ground water conditions of Clark County, Washington, with a description of a major alluvial aquifer along the Columbia River: U. S. Geological Survey Water Supply Paper 1600, 268 p.
Nance, W. B. and Taylor, S. R., 1976, Rare earth element patterns and crustal evolution: I. Australian post-Archean sedimentary rocks: Geochimica et Cosmochimica Acta, vol. 40, pp. 1539-1551.
Newton, V. C. Jr., 1969, Subsurface geology of the lower Columbia and Willamette Basins, Oregon: Oregon Department of Geology and Mineral Industries Oil and Gas Investigation, no. 2, 121 p.
Peck, D. L., Griggs, A.B., Schlicker, H. G., Wells, F. G., and Dole, H. M., 1964, Geology of the central and northern part of the Western Cascade Range in Oregon: U.S. Geological Survey Professional Paper 449, 56 p.
Priest, G. R., 1982, Overview of the geology and geothermal resources of the Mount Hood area, Oregon, in Priest, G. R., and Vogt, B. F., eds., Geology and Geothermal~esources of the Mount Hood Area, Oregon, Oregon Department of Geology and Mineral Industries Special Paper 14, pp. 6-15.
Priest, G. R., Beeson, M. H., Gannet, M. W., and Berri, D. A., 1982, Geology, geochemistry and geothermal resources of the Old Maid Flat area, Oregon, in Priest, G. R., and Vogt, B. F., eds., Geology and Geothermal Resources of the Mount Hood Area, Oregon, Oregon Department of Geology and Mineral Industries Special Paper 14, pp. 16-30.
78
Priest, G. R., Woller, N. M., Black, G. L., and Evans, S. H., 1983, Overview of the geology of the Central Oregon Cascade Range, in Priest, G. R., and Vogt, B. F., eds., Geology and geothermal~ resources of the Central Oregon Cascade Range, Oregon Dept. of Geology and Mineral Industries Special Paper 15, pp. 3-28.
Silvestri, S. C., 1961, Proposal for the genetic classification of hyaloclastites: Bulletin Volcanologique, vol. 25, pp. 315-321.
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Tolan, T. L., 1982, The stratigraphic relationships of the Columbia River Basalt Group in the lower Columbia River Gorge of Oregon and Washington: M. S. thesis (unpublished), Portand State University, Portland, Oregon, 15lp.
Tolan, T. L., and Beeson, M. H., 1984, Intracanyon flows of the Columbia River Basalt Group in the lower Columbia River Gorge and their relationship to the Troutdale Formation: Geological Society of America Bulletin, vol. 95, no. 4, pp. 463-477.
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. , 1963, Geology of Portland, Oregon and adjacent areas: U.S. Geological Survey Bulletin 1119, 119 p.
Van Atta, R. 0., and Kelty, K. B., 1985, Scappoose Formation, Columbia County, Oregon: New evidence of age and relation to the Columbia River Basalt Group: American Association of Petroleum Geologists Bulletin, vol. 69, pp. 688-698.
Waters, A. C. 1973, The Columbia River Gorge: basalt stratigraphy, ancient lava dams, and landslide dams, in Beaulieu, J. D., field trip chairman, 1973, Geolgic field tripS-in northern Oregon and southern Washington: Oregon Department of Geology and Mineral Industries Bulletin 77, pp. 133-162.
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79
Williams, I. A., 1916, The Columbia River Gorge: Its geologic history interpreted from the Columbia River Highway, Oregcn: Bureau of Mines and Geological Mineral Resources of Oregon, vol. 2, no. 3, 130 p.
Willis, R. F., 1977, Ground-water exploratory program, Bureau of Waterworks, Portland, Oregon: unpulished Portland Water Bureau report, 150 p.
Wise, W. S., 1969, Geology and petrology of the Mount Hood area: A study of High Cascade volcani~m: Geological Society of America Bulletin, vol. 80, pp.696-1006.
APPENDIX A
SAMPLE TYPE, UNIT AND LOCATION
INAA Experiment 7T
Sample Rock Type Unit Location
5-135 sed s Ttu Well 1N/3E 20CB2 5-145G vitrparate, vitric r=whole rock lithic or vitric sediment.
Unit Symbols: QTb=Boring Lava, Tb="upper Pliocene" basalt of the High Cascade Lavas, Ttu=upper Troutdale Formation, Ttl=lower Troutdale Formation, Tsr=Sandy River Mudstone.sed s Ttu " 5-440 sed s Ttu " 5-535 sed s Ttu " 5-585 sed s Ttl " 5-670 sed s Ttl II
5-710 sed s Ttl " 5-795 sed s Ttl " 5-970 sed s Ttl " 5-1100 sed s Ttl II
LSWSSB vitric r Ttu TlS, R4E, Sec 6, NW,SE 1160PMR vitric r Ttu TlN, R5E, Sec 27, NE,SE,NE SLTSSB vitric r Ttu TlS, R4E, Sec 6, NE,SW,NW CHPT Vitric r Ttu TlN, R4E, Sec 25, SW 700PMR sed w Ttl TlN, R5E, Sec 22, SE,SW,NW SRMGC sed w Tsr Tl S, R4E, Sec 11 , SE, NW, SE
INAA Experiment 7H
Sample Rock Type Unit Location
2-780 sed s Ttl Well 1N/3E 31CD 2-800 sed s Ttl " 2-820 sed s Ttl " 2-850 sed s Ttl " 2-870 sed s Ttl " 2-895 sed s Ttl " 2-925 sed s Ttl " 2-945 sed s Ttl " 2-975 sed s Ttl " 2-1000 sed s Ttl " 1-890 sed s Ttl/Ttu Well 1N/2E 29DA 1-935 sed s Ttl "
81
INAA Experiment 7H icontinued)
Sample Rock Type Unit Location
1-960 sed s Ttl Well 1N/2E 29DA 1-990 sed s Ttl " 1-1055 sed s Ttl " 1-1075 sed s Ttl " 1-1100 sed s Ttl " 1-1120 sed s Ttl " 1-1150 sed s Ttl " 1-1170 sed s Ttl " 1-1200 sed s Ttl " 3-240G vitric r Ttu, UTSA Well 1N/3E lSCB 3-348G vitric r Ttu, TSA " 3-387G vitric s Ttu, TSA " 3-549G vitric s Ttu, RC " 3-570G vitric s Ttu, RC " l-710G vitric r Ttu, TSA Well 1N/2E 29DA l-715G vitric r Ttu, TSA " l-915G vitric s Ttu, RC? " l-1125G vitric s Ttl, LRC " 2-435G vitric r Ttu, UTSA Well 1N/3E 31CD 2-600G vitric s Ttu, TSA " 2-750G vitric s Ttu, RC " 6-320G vitric s Ttu, TSA Well 1N/3E 33AD 6-345G vitric s Ttu, TSA " 6-571G vitric s Ttu, RC " 6-591G vitric s Ttu, RC "
INNA Experiment 7K
Sample Rock Type Unit Location
HR-lB basalt Tb T3N, RlOE, Sec 33, NW,NW,NW; West Hood River palagonite complex
Gordon Creek Rd. section TB-3G vitric s Ttu, TSA TIN, R3E, Sec 20, NE,SW,NE
Taggart Bluff, I/3 mile NE of Blue Lake
BL-2G vitric s Ttu, TSA TIN, R3E, Sec 20, SE,NE,NW West end of Blue Lake
P28-37SG vitric s Ttu, TSA Production well P28 T34-390G vitric s Ttu, TSA Test well T34 GCR-2F sed s Tsr TIS, R4E, Sec NW,SE,SE,NE GCR-2C sed w Tsr TIS, R4E, Sec NW,SE,SE,NE
Rock Type Symbols: Sed s=-200 seived sediment, sed w=whole rock sediment, vitric s=vitric separate, vitric r=whole rock lithic or vitric sediment.
82
Unit Symbols: QTb=Boring Lava, Tb="upper Pliocene" basalt of the High Cascade Lavas, Ttu=upper Troutdale Formation, Ttl=lower Troutdale Formation, Tsr=Sandy River Mudstone.
APPENDIX B
GEOCHEMICAL ANALYTICAL PROCEDURE AND
ELEMENTAL CONCENTRATION TABLES
Samples were analyzed in three experiments. Experiment 7T was
conducted in spring 1983 as part of a required project for Advanced
Geochemistry (G519). Steve Davis and Matt McClincey assisted in the
experiment. Twenty-two samples were analyzed: Thirteen sediment and
three hyaloclastite separates from Exploratory Well 1N/3E 20CB2 (number
5) along with six sediment samples collected from outcrops of the
Troutdale Formation and Sandy River Mudstone. Thirty-seven well
cutting samples were analyzed in experiment 7H in fall 1984. Twenty
one were sediment samples and sixteen were hyaloclastite separates.
Wells sampled included 1N/2E 29DA (number 1), 1N/3E 31 CD (number 2),
1N/2E 15 CB (number 3) and 1N/3E 33AD (number 6). Sample numbers for
well samples in experiments 7T and 7H correspond to well number (1, 2,
3, 5, or 6) and sample depth from ground level in feet. Experiment 7K
was performed in spring 1985. The twenty-eight samples analyzed were
primarily field samples with a few well samples. A description of
samples and their location can be found in Appendix A.
Well sediment was wet seived to -200 mesh and dried in porcelain
dishes. Hyaloclastite glass separates were picked from cuttings or
hand sample using a jewelers tweezers under a binocular microscope.
Three to six grams of vitic clasts per sample were obtained by
selecting grains lacking weathering rinds or cemented fine grained
84
sediment attached. All vitric separates were washed in a solution of
calgonite and water in an ultrasonic cleaner and rinsed with tap water.
Whole sediment samples in experiments 7T and 7K were easily
disaggregated for splitting and weighing. Basalt samples analyzed in
experiment 7K were crushed in a steel jaw crusher. Clean unweathered
chips were then selected for analysis.
Samples were crushed in a hardened steel mortar and pestal used
only for INAA sample preparation. Samples were split down to about one
gram by halving a pile poured onto two weighing papers. Each sample
was then placed in a pre-weighed polyethelene vial for irradiation.
Sample and vial were then weighed to +or- .0002 grams to obtain the net
sample weight.
Standards BCR-1 and W-1 were used in experiment 7T. Standards
BCR-1 and PCC-1 were used in experiments 7H and 7K. Values for element
concentrations in the standards were taken from Flanagan (1976).
Samples and standards were irradiated for one hour in Reed College's
TRIGA Mark II reactor. Irradiation produces unstable radionuclides by
neutron bombardment. One of the products of decay of these unstable
isotopes is gamma radiation. Each isotope has a characteristic energy
spectrum when counted on a Ge-Li detector which in this case is
connected to Tracor Northern hardware and software. Each sample, when
counted, produces a spectum consisting of peaks that represent
individual radioisotopes. Peak intensities are relative to the
concentration of radionuclides in the sample.
The Tracor Northern software analyzes each samples spectrum to
determine the net count of each peak and the counting error as a
85
percentage by comparing the peak's shape to an ideal bell-shaped curve.
Elemental concentrations are determined for each sample by a program in
the Portland State University's main frame Honeywell computer. The
program compares net counts and percent error of peaks along with
weight and decay time for each sample to those of the standards to
calculate elemental concentrations and one standard deviation.
EXP
7T
G51
9 1S
T
CT
SAM
PLE
NA
K
5-13
-5
----
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20
2.
00
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9
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1
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7 __
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5
1 •
41
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2.1
4
0.0
1
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5-4
0L
1
.46
0
.01
1
.15
5
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0
1.7
5
0.0
1
1.4
0
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.4
o
5-5
85
1
. 70
o.
01
1.9
0
5-6
70
1
.81
0
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1
.90
5-
71()
1
.86
0
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1
.70
5
-75
0
1.7
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1.7
0
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-79
5
1.6
4
a-~ 0
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. 9o
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70
1
.62
0
.01
1
.60
0.3
0
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0.1
5
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0.1
9
o.
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8
0.2
0
0.2
0
0.3
0
36
.10
2
7.6
0
22
.30
5
.60
3
5.0
0 LA
8.4
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36
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3
3.2
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27
.80
3
2.2
0
0.6
0
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50
0.3
0
0.6
0
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0.6
0
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0
32
.10
0
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0
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. 30
--
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.00
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0 0
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6
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7
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0
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4.5
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4.6
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0.0
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0.0
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3
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4
0.0
3
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4
0.0
5
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78
.00
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100
APPENDIX C
CROSS-SECTIONS OF WELL AREA
Figure 24. Location of cross-sections in Appendix C.
